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Zeitschrift/Journal: Jahrbuch der Geologischen Bundesanstalt

Jahr/Year: 1995

Band/Volume: 138

Autor(en)/Author(s): Dommergues Jean-Louis, Meister Christian, Böhm Florian

Artikel/Article: New Data on Austroalpine Liassic Ammonites from the Adnet Quarries and Adjacent Areas (Oberösterreich, Northern Calcareous Alps) 161-205 ©Geol. Bundesanstalt, Wien; download unter www.geologie.ac.at

JAHRBUCH DER GEOLOGISCHEN BUNDESANSTALT Jb. Geol. B.-A. ISSN 0016–7800 Band 138 Heft 2 S. 161–205 Wien, August 1995

New Data on Austroalpine Liassic Ammonites from the Adnet Quarries and Adjacent Areas (Oberösterreich, Northern Calcareous Alps)

JEAN-LOUIS DOMMERGUES, CHRISTIAN MEISTER & FLORIAN BÖHM*) 17 Text-Figures and 10 Plates

Austria Eastern Alps Austroalpine Liassic Österreichische Karte 1 : 50.000 Ammonites Blätter 63, 64, 93, 94 Biostratigraphy

Contents

Zusammenfassung ...... 161 Abstract ...... 162 Résumé ...... 162 1. Introduction ...... 162 2. Regional Setting ...... 162 3. Lithological Description and Qualitative/Quantitative Ammonite Distribution ...... 163 3.1. Adnet Quarries ...... 163 3.1.1. Quarry 31 (Rotgrauschnöllbruch) ...... 164 3.1.2. Quarry 12 (Lienbacherbruch) ...... 164 3.1.3. Quarry 28 (Kiefer-Plattenbruch) ...... 166 3.1.4. Quarry 41 (Deislbruch) and Quarry 38 (Wolfgruberbruch) ...... 166 3.2. Additional Outcrops of the Osterhorn Block ...... 166 3.2.1. Glasenbach Gorge ...... 166 3.2.2. Wetzsteingraben ...... 168 4. Systematic Paleontology ...... 169 5. Biostratigraphical Framework ...... 178 6. Conclusion ...... 182 Acknowledgements ...... 182 Plates 1–10 ...... 182 References ...... 202

Neue Daten zu ostalpinen Lias-Ammoniten aus Adnet und Umgebung (Oberösterreich, Nördliche Kalkalpen) Zusammenfassung Biostratigraphische Untersuchungen in den Steinbrüchen von Adnet (Salzburg) ermöglichen uns die Unterscheidung von 11 Faunenhorizonten im Ober-Hettang/Sinemur des Oberostalpins. Die regional sehr begrenzte Verbreitung von vielen der gefundenen Unterlias-Ammoniten [z.B. Adnethiceras adnethicus (HAUER), Gleviceras doris sensu PIA] und die noch sehr lückenhafte biostratigraphische Abfolge erschweren sowohl lokale Korrelationen als auch Vergleiche mit NW-Europa, dem Mittelostalpin und den Apenninen. Die Pliensbach-Fauna des Wetzsteingrabens zeigt dagegen sehr große Ähnlichkeiten zu anderen, zeitgleichen Ammoniten-Vorkommen des Oberostalpins und fügt sich zudem sehr gut in die biostratigraphischen Standard- gliederungen für den euroborealen und tethyalen Raum ein.

*) Author’s addresses: Dr. JEAN-LOUIS DOMMERGUES, Centre de Paléontologie analytique et Géologie sédimentaire, URA CNRS 157, Centre des Scien- ces de la Terre de l’Université de Bourgogne, 6 Bd Gabriel, F-21000 Dijon; Dr. CHRISTIAN MEISTER, Muséum d’Histoire Naturelle de Genève, Départe- ment de Géologie et Paléontologie, 1 Rte de Malagnou, cp 6434, CH-1211 Genève; Dr. FLORIAN BÖHM, Palaöntologisches Institut, Universität Erlangen, Loewenichstraße 28, D-91054 Erlangen.

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Abstract The biostratigraphic studies of ammonites from the Adnet quarries allow to propose a set of 11 horizons or levels for the Upper Austroalpine Late Hettangian–Sinemurian. The originality of the faunal assemblages [e.g. Adnethiceras adnethicus (HAUER), Gleviceras doris sensu PIA] and the disconti- nuity of the biostratigraphical sequence make local comparisons and correlations with NW Europe, the Middle Austroalpine and the Apennines rather difficult. By contrast, the Pliensbachian fauna from Wetzsteingraben presents a clear faunal homogeneity with the other studied regions of the Upper Austroalpine. Moreover, they well integrate with the Euroboreal and Tethyan standard biostratigraphical framework.

Nouvelles données sur les ammonites liasiques de l’Austroalpin pour les carrières d’Adnet et les régions adjacentes (Autriche, Alpes Calcaires septentrionales) Résumé L’étude des ammonites dans les carrières d’Adnet permet de proposer une série de 11 horizons ou niveaux pour l’Hettangien supérieur et le Sinémurien de l’Austroalpin supérieur. L’originalité des assemblages fauniques [e.g. Adnethiceras adnethicus (HAUER), Gleviceras doris sensu PIA] et la discontinuité de la séquence biostratigraphique rendent parfois difficiles les comparaisons locales et les corrélations avec l’Europe du nord-ouest, le domaine de l’Austroalpin moyen et les Apennins. Les faunes pliensbachiennes du Wetzsteingraben présentent par contre une nette homogénéité pour les associations fauniques avec les autres régions de l’Austroalpin supérieur et elles s’intègrent aisément dans les cadres biostratigraphiques propo- sés pour le domaine euroboréal et le domaine téthysien.

1. Introduction The Adnet area is part of the Osterhorn block, displaying unusually mild tectonic disturbance compared with other This paper is a complement to the recent study of MEIS- parts of the Northern Calcareous Alps. The Osterhorn TER & BÖHM (1993). It’s intention is to improve the Block is a part of the Tyrolic nappe system (Text-Fig. 1). Sinemurian and Pliensbachian stratigraphy of the North- Detailed desriptions of the settings of the Osterhorn ern Calcareous Alps. We present results from modern tax- Mountains are provided by TOLLMANN (1976b), PLÖCHINGER onomic and biostratigraphic investigations of a famous (1990) and BÖHM (1992a). classical site of stratigraphic research: the quarries of Ad- net, and of two other localities of the Osterhorn block: the Glasenbach Gorge and the Wetzsteingraben.

2. Regional Setting The quarries of the little village of Adnet, situated ap- proximately 10 km southeast of the city of Salzburg (Aus- tria), are the type locality of the Liassic Adnet Formation (Text-Fig. 1). This is a sequence of red limestones and marls, up to some 30 m thick, starting in the upper Het- tangian and per definitionem passing over into the Middle Jurassic Klaus Formation at the end of the Liassic (KRYS- TYN, 1971). Rich ammonite faunas provided by the Adnet Lime- stones and excellent exposures available from the century old quarrying made Adnet a famous site of the stratigraphic pioneers during the second half of the 19th century (LIPOLD, 1851; HAUER, 1853, 1854, 1856; WÄHNER, 1882–98, 1886, 1903; AMMON, 1893; PIA, 1914). Surpris- ingly, in the 20th century very few papers about facies, stratigraphy or ammonite faunas of the Liassic of Adnet were published (WIEDMANN, 1970; KRYSTYN, 1971; WENDT, 1971). Some short reports and a geological map of the area were presented by SCHLAGER (1957, 1967, 1968, 1969, 1970) and SCHLAGER & SCHLAGER (1960). TOLLMANN (1976a) shortly discusses stratigraphy and facies of the Adnet For- mation. KIESLINGER (1964) presents a complete list of the Adnet quarries with short lithological descriptions. Some papers dealing with special sedimentological aspects of the Adnet Formation were presented by HALLAM (1967), JURGAN (1969), HUDSON & JENKYNS (1969), HUDSON & COLE- MAN (1978), BÖHM (1992b) and BÖHM & BRACHERT (1993). But they discuss stratigraphic aspects at most very brief- ly. Some new attempts to decipher the litho- and biostra- Text-Fig. 1. tigraphy of the Adnet Formation at its type locality can be Regional overview of the study area in the Osterhorn Mountains. found in BÖHM (1992a), MEISTER & BÖHM (1993) and BÖHM Studied outcrops indicated by stars. et al. (in press). Tectonic map after TOLLMANN (1976b).

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Text-Fig. 3. Road map of the Adnet area showing the locations of the investigated quarries. Quarry numbers refer to KIESLINGER (1964).

3. Lithological Description and Qualitative/Quantitative Ammonite Distribution 3.1. Adnet Quarries The quarries of Adnet expose Late Triassic to late Lias- sic limestones. The Late Triassic (Rhaetian) reefs of Adnet are very famous for their coral thickets partly preserved in growth position. These reef limestones are overlain by Liassic hemipelagic deep-water limestones (BÖHM, 1992a,b; BÖHM & BRACHERT, 1993), which are partly rich in ammonites. In most sections the base of the Liassic limestone series is formed by a few centimetres of condensed red limestone overlain by a ferromanganese crust of upper Het- Text-Fig. 2. tangian age (WENDT, 1971; BÖHM, 1992a). Above the crust Stratigraphic setting of the study area in the Osterhorn Mountains. follows a series of red micritic, mostly nodular limestones, The stratigraphic range of the studied sections is marked by black bars. up to 13 m thick. They are erosively overlain by a thick de- Wetz. = Wetzsteingraben; G. = Glasenbach Gorge. bris flow deposit called Scheck breccia (BÖHM et al., in Lithostratigraphic framework after BÖHM et al. (in press). press). The nodular limestones are known from sections in the sur- roundings to be of Sinemurian to Carixian age (MEISTER & BÖHM, 1993), but due to the erosion by the Scheck debris flows Carixian and uppermost Sinemurian are lacking in most Adnet quarry sections (BÖHM et al., in press). The nodular limestones of Adnet therefore belong to the Sinemurian Schmied- wirt Member of the Adnet Forma- tion following the lithostratigraphy proposed by BÖHM et al. (in press) for the Osterhorn Mountains (Text-Fig. 2). We could not find the strongly marly nodular limestones of the overlying Kehlbach Member (Carixian), which are well exposed in sections north of the Adnet quarries. At Adnet we sampled the upper Hettangian ferromanganese crust and several levels of the

Text-Fig. 4. Adnet (quarry 31, Rotgrauschnöllbruch; SW part) lithological profile and ammonite ranges.

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Text-Fig. 5. Adnet (quarry 12, Lienbacherbruch; NW part) lithological profile and ammonite ranges.

nodular limestones providing ammonite faunas. For the identification of individual quarries we refer to the numbers and quarry names of KIESLINGER (1964). Locations are shown in Text-Fig. 3. Details on the microfa- cies and regional situation of the Adnet area were recently given by BÖHM (1992a).

3.1.1. Quarry 31 (Rotgrauschnöllbruch) This quarry exposes the Upper Hettangian ferromanganese crust (“Brandschichte”, GALLET et al., 1993: Text-Fig. 2). The quarry is still active. The section shown in Text-Fig. 4 was profiled in April 1993 in the southwestern corner of the quarry and has been cut away since then. The ferromanganese crust rests on about 1 m of massive red-grey crinoidal limestone of middle to upper Hettangian age (WÄHNER, 1886; GALLET et al., 1993), which thickens to several metres towards the north. All ammonites collected were embedded in the ferromanganese matrix. The crust is overlain by the red nodular limestones of the Ad- net Formation with another ferromanganese crust and a horizon of deep-water stromatolites about half a metre above the Hettangian crust (BÖHM & BRACHERT, 1993). The Upper Hettangian hardground can be found in many of the Adnet quarries, in many other localities of the Osterhorn block and even in other parts of the Northern Calcar- eous Alps (WENDT, 1971; BLOOS, 1988; BÖHM, 1992a). It forms a very useful marker bed in the Osterhorn Mountains and probably origi- nated from submarine omission during a eustatic sea-level lowstand (BÖHM, 1992b).

3.1.2. Quarry 12 (Lienbacherbruch) A special thick bedded facies of the Adnet Formation with few nodular layers and abun- dant encrusted intraclasts (“Hartgrundklas- ten”, BÖHM, 1992a: 87) occurs near the top of the drowned Rhaetian Adnet reef. It is exposed in the active quarry 12. The section of Text-Fig. 5 was profiled in June 1992 in the northwestern part of the quarry. We found an ammonite-rich level in a slightly marly, thin- bedded layer resting on 4.7 m of decimetre- bedded red limestones. Overlying the marly layer 2–3 m of red limestones are exposed. The upper Hettangian ferromanganese crust forms the base of the Liassic limestones (WENDT, 1971: Fig. 3). The marker layer of deep-water stromatolites, also found in quarry 31, lies about 3 m below our ammonite-rich level in this part of the quarry. GAL- LET et al. (1993) report Arnioceras, Asteroceras and Oxynoticeras from the lower part of the section.

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Text-Fig. 6. Adnet (quarry 28, Plattenbruch) lithological profile and ammonite ranges. The section exposes thin-bedded red nodular limestones overlain by the Scheck breccia. Only major bedding planes are shown.

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3.1.3. Quarry 28 (Kiefer-Plattenbruch) Quarry 41 was described by WENDT (1971). It exposes This active quarry is situated in the northern part of the the same slightly marly red nodular limestones (Schmied- Adnet quarry area. It is the thickest Liassic section ex- wirt Mb.) seen in quarry 28. Again they are erosively cut by posed at Adnet (Text-Fig. 6) with about 13 m of thin-bed- the overlying Scheck breccia (BÖHM et al., in press: Fig. 5). ded, slightly marly, nodular red Adnet Limestones of the Compared to quarry 28 the thickness of the nodular lime- Schmiedwirt Member (mainly MF6 of BÖHM, 1992a), dis- stones is reduced to only 7 m (41, central part), 8 m (41, conformably overlain by a several metres thick “Scheck” NW part) and 10 m (quarry 38). Considering our biostrati- breccia layer (Scheck Member). The erosive contact is graphic results, this can be explained by stronger erosion clearly visible near the top of the sawn quarry wall. by debris flows. The base of the nodular limestones is formed by a ferro- The base of the nodular limestones is formed by the Up- manganese crust, which was exposed some years ago. per Hettangian ferromanganese crust (“Brandschichte”), Unfortunately, due to a fault between this exposure and which from time to time becomes exposed on the floor of the upper part of the section the exact position of the ba- quarry 41 (WENDT, 1971). We found ammonites in the up- sal crust is unknown. per part of the nodular limestones, in a marl rich interval The nodular limestones of the Schmiedwirt Member starting about 7 m above the basal crust. show a bedding hierarchy, well visible on the sawn walls. Most beds are 5–15 cm thick with few exceptions of up to 0.5 m. Many of these beds have rather indistinct bedding planes, which may vanish laterally on a scale of some 3.2. Additional Outcrops metres. The thin beds form packages of about 1 to 2.5 m of the Osterhorn Block thickness, bordered by major marly partings. Some of Two additional locations in the northern and southern these packages show an internal organization with up- part of the Osterhorn block were investigated to enlarge ward thinning and increasing nodularity. Seven packages our data base. Both sections represent Liassic basinal are visible on the quarry wall (Text-Fig. 6). settings. Both the Glasenbach and the Wetzsteingraben section show very complex tectonic structures due to intra-Jurassic gravity sliding. For the Wetzsteingraben the 3.1.4. Quarry 41 (Deislbruch) connection with the Tauglboden Formation allows to date and Quarry 38 (Wolfgruberbruch) the sliding as Late Jurassic. In the Glasenbach section the Both quarries are situated 1.5 km northeast of the vil- situation is less clear. Both Early and Late Jurassic ages or lage of Adnet near the Wolfgrub farmhouses. Quarry 41 combinations of them are possible. Detailed biostrati- (Text-Fig. 7) is still working, quarry 38 (Text-Fig. 8), which graphy may help to solve this problem. Our results provide is situated about 100 m north of quarry 41, is abandoned. a first step.

3.2.1. Glasenbach Gorge The Glasenbach Gorge is situated 8 km north of Adnet, in the southeastern outskirts of the city of Salzburg (Text-Figs. 1, 9). There, in the northwestern part of the Osterhorn block, grey basinal limestones (Scheibelberg Fm., Text- Fig. 2) were deposited during the Sinemurian, while red limestones of the Adnet Formation formed in the Adnet area (BÖHM, 1992a: Fig. 62). The Glasenbach section displays the most basinal part exposed there. The gorge exposes more than 300 m of WNW dipping Sinemurian–Oxfordian sediments, un- conformably overlain by an Upper Cretaceous conglomerate (Gosau) in the western part of the gorge (PREY, 1969). Sedimentary succession and tectonic structure were described in detail first by FUGGER (1906) and later by VORTISCH (1970) and BERNOULLI & JENKYNS (1970). Some short reports with additional information were provided by DEL-NEGRO (1958, 1979). We will give only a short description of the lower part of the exposed section, which is relevant for the stratigraphic context of the ammonite-bearing strata.

Text-Fig. 7. Adnet (quarry 41, Deislbruch) lithological profile and ammonite ranges. Thin-bedded red nodular limestones overlain by the Scheck breccia. Only major bedding planes are shown.

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Text-Fig. 8. Adnet (quarry 38, Wolfgruberbruch) lithological profile and ammonite ranges. Thin-bedded red nodular limestones overlain by the Scheck breccia.

The section starts in the easternmost part of the gorge VORTISCH (1970) and DEL-NEGRO (1979) relying on FUGGER with grey limestones with darkgrey spots, (“Fleckenkalk”). (1906) mention Arnioceras ceratitoides (QUENSTEDT) and Echio- ceras raricostatum (ZIETEN) from this unit. It thus could com- prise the Middle to Late Sinemurian. A steep fault separates this unit from lightgrey cherty Scheibelberg limestone to the west. VORTISCH (1970) found Arnioceras near the top of this unit. The top is formed by a huge layer of slump masses (BERNOULLI & JENKYNS, 1970: Pl. 5/2) containing Hettangian sediments. BERNOUL- LI & JENKYNS (1970) interpreted this and other slump com- plexes of the section as synsedimentary mass flows. The slump mass is overlain by grey slightly cherty limestones (Text-Fig. 10) similar to those found below. Another slump complex forms the upper boundary of this 12 m thick layer, which in it s middle third contains many ammonites. Above the upper slump mass some 10 m of Schei- belberg Limestone (Middle or Upper Sinemurian, VOR- TISCH, 1970) pass abruptly into red marly nodular limestones of the Adnet Formation (Kehlbach Member, Ca- rixian). We investigated the 12 m thick limestone layer intercalated between the two slump masses (limestones left of “1B” in BERNOULLI & JENKYNS, 1970: Fig. 1). This unit is well exposed in the river bed, west of the ichtyosaur pla- Text-Fig. 9. que. The limestones overlie the irregular surface of the Location of the studied section (arrow) in the river bed of the Klausbach lower slump masses (Text-Fig. 10). The contact is formed in the Glasenbach Gorge. by some centimetres of black calcareous shale. The upper

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Text-Fig. 10. Glasenbach lithological profile and ammonite ranges. The section outcrops in the river bed west of the ichtyosaur plaque. The ammonite-rich grey limestones are intercalated between two slump masses.

slump mass overlying the limestones is a breccia with marly matrix and few lightgrey components. It s top is formed by a hard massive component-rich bed with a sparitic crinoidal matrix. The breccia can be seen to pass into slump masses above the road along the river. The limestones consist of 10 to 40 cm thick beds of lightgrey, partly greenish, bioturbated wackestones with ostracodes, sponge spicules and radiolarians (MF4, BÖHM, 1992a). Small violett-red spots occur occa- sionally. Bedding planes are due to grey marl partings of up to 5 cm. Rare thicker marl in- tervals (up to 15 cm) contain thin limestone layers. Ammonites occur on bedding planes and within the limestone beds. A 1 m thick marly breccia layer is intercalated near the top of the limestone unit. According to BERNOULLI & JENKYNS (1970) the limestone unit should represent the nor- mal autochthonous sedimentation between two intra-Sinemurian events of gravitational mass flows. On the other hand VORTISCH (1970) stressed the repetition of stratigraphic levels in the limestone units separated by the slump masses. The model of gravitational mass flows is largely accepted today. But, if VORTISCH was right, our limestone unit must represent a large allochthonous slide. Then, most of the grey limestones exposed in the Glasenbach gorge may be part of a large mass flow, that took place at the end of the Sinemurian as assumed by BÖHM (1992a), or alternatively, of an even much larger event of Early Toarcian or Late Jurassic age. Neither the stratigraphic data collected by VORTISCH (1970) nor the sedimentological data available at the moment allow to prove one of these possibilities. Bedding attitude below (275/20) and above (290/20) the upper slump mass are not significantly different.

3.2.2. Wetzsteingraben The Wetzsteingraben is the most remote tributary of the Königsbach, situated in the eastern part of the Osterhorn block, 16 km east of Adnet (Text-Figs. 1, 11). It can be ac- cessed from Abersee at the southern side of Lake Wolfgang. The Wetzsteingraben reaches the Königsbach some hundred metres southwest of the famous Kendlbachgraben (Rhaetian–Hettangian boundary). We investigated an outcrop southeast of the creek at the forest road, which crosses the Wetzsteingraben at about 870 m. Short descriptions are given by PLÖCHINGER (1977,

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kogel near Bad Ischl (SCHÄFFER & STEIGER, 1986; MEISTER & BÖHM, 1993) and about 150 km to the east at the Luft- straße section near Kirchberg (BÖHM, 1992a: 179). Ob- viously red facies occurred in many basinal areas during the early or middle Carixian. The occurrences are con- temporary with an onset of increased tectonic activities in many parts of the Northern Calcareous Alps (BÖHM et al., in press). The transition to red facies was caused by reduced sedimentation rates (MEISTER & BÖHM, 1993: Fig. 8). Re- duced rates of sediment deposition in basinal settings may have resulted from: 1) A change in the patterns of sediment distribution by gravitational transport and currents. 2) Increased erosion by gravity flows. Text-Fig. 11. 3) Changes in subsidence patterns creating new sinks Location map for the Wetzsteingraben. and thereby starving former ones. The studied section is located at the forest road east of the Wetzsteingra- ben (arrow).

1982: 65f). A very detailed but hardly readable description 4. Systematic Paleontology of the Wetzsteingraben is provided by VORTISCH (1960). We sampled a large olistolith of red Liassic marl and limestone Remark (Adnet Fm.), very rich in ammonites, embedded in brec- This paper is a complement to the study of MEISTER & cias and cherts of the Late Jurassic Tauglbodem Forma- BÖHM (1993). Descriptions and discussions detailed there tion. The olistolith consists of red marls and red (rarely will not be repeated here. So, for the well-known taxa we grey) limestone beds. Both show clear signs of strong refer the reader to MEISTER (1986, 1989), DOMMERGUES & bioturbation. Some burrows are discernible. Echinoderm MEISTER (1987 a/b, 1989 a/b, 1990a), MEISTER & LOUP content is rather low. The limestone beds are biomicrites (1989), DOMMERGUES et al. (1990, 1994), BLAU & MEISTER (wackestones), some with ostracodes and sponge (1991), MEISTER & BÖHM (1993). The rich material collected spicules (MF5, BÖHM, 1992a). Graded crinoidal turbidite in the Adnet quarries and new data on the Tethyan beds with thin basal lithoclastic layers occur (MF25a, Sinemurian from the Central Apennine give us a better un- BÖHM, 1992a). Red crinoidal, strongly bioturbated marls derstanding of the variability of Arnioceras and Asteroceras with large burrows of Zoophycos outcropping to the right and let us precise their systematic position. But with few of the marly limestones did not yield ammonites. exceptions the taxonomy agrees well with all our previous PLÖCHINGER (1982) reported Prodactylioceras sp. from the papers. ammonite-rich, red marly limestones pointing to a Pliens- bachian age. He ascribed them to the Saubachschichten, a common Toarcian lithological unit of the Osterhorn Mountains (Saubach Mb, Text-Fig. 2). Suborder: Phylloceratina ARKELL 1950 The low echinoderm content of limestone beds and Superfamily: Phyllocerataceae ZITTEL 1884 most marls, the lack of “filaments” (planktonic bivalves) as Family: Phylloceratidae ZITTEL 1884 well as the frequent occurrence of sponge spicules con- Subfamily: Phylloceratinae ZITTEL 1884 tradict the assignment to the Saubach member sensu BÖHM et al. (in press). The high marl content, the presence Genus: Phylloceras SUESS 1865 of lithoclastic turbidites and the Pliensbachian age allow Type species: Ammonites heterophyllus SOWERBY 1820. to assign these series to the Kehlbach member (Text- Fig. 2). There is also facial and stratigraphic correspon- dence to red marly limestones of middle Carixian to lower Domerian age, overlying grey basinal Fleckenmergel at the Phylloceras sp. Rötelstein (MEISTER & BÖHM, 1993). (Pl. 1, Fig. 1) Several Liassic lithologies are found as olistoliths within We regroup here a Hettangian Phylloceratid with a quite the Upper Jurassic Tauglboden breccias of the Königs- opened umbilicus (O/DՆ12 %). bach area. Large olistoliths of basinal grey Liassic Flek- Local range: marmorea horizon, Hettangian–Sinemurian kenmergel are most common (VECSEI, 1986). The olistoliths are thought to have slided northward into the Late (Adnet quarry 31). Jurassic Tauglboden basin (SCHLAGER & SCHLAGER, 1973) from a former basinal area at the southern rim of the Osterhorn block, transformed into the Trattberg high dur- Phylloceras cylindricum (SOWERBY, 1833) ing late Jurassic (discussion in BÖHM, 1992a: 133, 147). (Pl. 1, Fig. 3) The stratigraphic succession of this Liassic basin probably was similar to that of the Rötelstein (MEISTER & BÖHM, 1833 Ammonites cylindricum SOWERBY, 1812–46, p. 333, Fig. 62. 1993) with grey Fleckenmergel passing into red marly 1901 Phylloceras cylindricum (SOWERBY). – FUCINI, Pl. 2, Fig. 6–8. 1901 Phylloceras cylindricum var. bielzii H ERB. – FUCINI, 1901–05, Pl. 3, limestones during middle Carixian. The red facies prob- Fig. 1–4. ably lasted at least until the Toarcian. Very similar succes- 1994 Phylloceras cylindricum (SOWERBY). – DOMMERGUES, FERRETTI & sions are found again in other Liassic basins: at the Rot- MEISTER, Pl. 1, Fig. 1–2.

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We regroup here some Sinemurian Phylloceras charac- Local range: rejectum horizon, Obtusum zone (Adnet terized by parallel whorlsides and by low rounded venter. quarry 38). This morphology persists during all the ontogeny. This kind of morphology is also close to juvenile P. (Hantkeniceras) but in this subgenus the intermediate and adult whorl- sections become more inflated. Genus: Partschiceras FUCINI 1923 Local range: gr. paucicostatum horizon Parasteroceras sp. Type species: Ammonites Partschi STUR 1851. horizon (Early Sinemurian Late Sinemurian) [Adnet quarries 28, 38, 41].

Partschiceras gr. striatocostatum (MENEGHINI 1853) (Pl. 1, Figs. 9, 12) Phylloceras gr. frondosum – hebertinum (REYNÈS 1868) 1851 Ammonites Partschi STUR, p. 26 (nom. nudum). 1853 Ammonites striatocostatus MENEGHINI, p. 28. 1868 Ammonites Hebertinus REYNÈS, Pl. 2, Fig. 3. 1868 Ammonites Sturi REYNÈS, Pl. 3, Fig. 1. Ammonites frondosus REYNÈS, Pl. 5, Fig. 1. 1913 Phylloceras anonynum HAAS, Pl. 1, Fig. 5. 1884 Phylloceras Meneghinii GEMMELLARO, Pl. 2, Fig. 13–17. 1977 Partschiceras sturi (STUR). – WIEDENMAYER, Pl. 2, Fig. 6, 7; Pl. 5, 1989 Phylloceras frondosum (REYNES). – MEISTER, Pl. 2, Fig. 1, 2 with Fig. 1–4 with synonymy. synonymy. Partschiceras striatocostatum (MENEGHINI). – WIEDENMAYER, Pl. 4, Phylloceras hebertinum (REYNES). – MEISTER, Pl. 2, Fig. 5, 7 with Fig. 5–8 with synonymy. synonymy. 1993 Partschiceras striatocostatum (MENEGHINI). – MEISTER & BÖHM, 1993 Phylloceras gr. frondosum (REYNES). – MEISTER & BÖHM, Pl. 2, Pl. 2, Fig. 4 with synonymy. Fig. 1, 2. We put in affinity with P. striatocostatum (MENEGHINI) several Only one exemplar from Wetzsteingraben can be put fragments of a compressed Phylloceratidae characterized close to the P. frondosum – hebertinum group. The fragmentary in the adult stages by rectiradiate, blunt ribs and fine sample shows an intermediate morphology between the striae on the high part of the sides and on the venter. broad whorl section of P. hebertinum (REYNES) and the nar- An example from the lower part of the Late Sinemurian row one of P. frondosum (REYNES). (Glasenbach) perhaps could be also brought near the Local range: algovianum horizon, Margaritatus zone MENEGHINI’s species. (Wetzsteingraben). Local range: rejectum horizon algovianum level (Ob- tusum Margaritatus zones) [Adnet quarry 38, Glasen- bach, Wetzsteingraben]. Subgenus: Calliphylloceras SPATH 1927

Type species: Phylloceras disputabile ZITTEL 1869. Family: Juraphyllitidae ARKELL 1950

P. (Calliphylloceras) bicicolae (MENEGHINI 1874) (Pl. 1, Fig. 11) Juraphyllitidae sp. (Pl. 1, Fig. 2) 1874 Phylloceras Bicicolae MENEGHINI, p. 106. 1989 Calliphylloceras bicicolae (MENEGHINI). – MEISTER, Pl. 2, Fig. 3, 4 Some poorly preserved specimens can be attributed to with synonymy. the earlier members of that family. They come from the fer- 1993 Calliphylloceras bicicolae (MENEGHINI). – MEISTER & BÖHM, Pl. 1, romanganese level near the base of the Adnet limestones Fig. 2, 5. at Adnet (marmorea horizon, Hettangian Sinemurian) (Ad- These strongly periodically constricted Phylloceras are at- net quarry 31). tributed to the long range species P. (C.) bicicolae (MENE- GHINI). If this species, even the genus, are well known during the Pliensbachian and the Toarcian, their distribution still stays episodic during the Sinemurian. Genus: Juraphyllites MÜLLER 1939

Local range: rejectum horizon isseli level (Obtusum Type species: Phylloceras diopsis GEMMELLARO 1884. Margaritatus zones) [Adnet quarry 38, Wetzstein- graben]. Juraphyllites nardii (MENEGHINI 1853) (Pl. 1, Fig. 6)

Subgenus: Zetoceras KOVÁCS 1939 1853 Ammonites Nardii MENEGHINI, p. 27. 1866 Ammonites transylvanicus HAUER, p. 192. Type species: Ammonites zetes d’ORBIGNY 1850. 1901 Rhacophyllites nardii (MENEGHINI). – FUCINI, Pl. 7, Fig. 1–7. Rhacophyllites nardii var. dorsocurvata FUCINI, Pl. 8, Fig. 7. 1993 Juraphyllites nardii (MENEGHINI). – MEISTER & BÖHM, Pl. 2, P. (Zetoceras) sp. Fig. 8, with synonymy. (Pl. 1, Fig. 4) The Juraphyllites regrouped here are characterized in the adult ontogenetic stages by well developed ribs from the We regroup here some Phylloceratina characterized by lower part of the flank or at least from the periumbilicus an involute shell, a compressed whorl section with slightly edge. convergent sides towards the extern part, a narrow ventral Large Sinemurian specimens can attain a great size, area and a highly complex suture line. more than 15 cm diameter.

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Local range: Parasteroceras sp. horizon, Raricostatum differences between them are inconsistent, concerning zone (Adnet quarry 28, Glasenbach). mainly rib density, whorl section and tubercles. Taking in account the rib density A. adnethicum (HAUER) presents an intermediate morphology between A. ferstli Juraphyllites libertus (GEMMELLARO 1884) (HAUER), a more spaced ribbed form (HAUER 1854, Pl. 2), (Pl. 1, Fig. 5) and A. herbichi (BONARELLI), a closer ribbed form. Moreover A. haueri WIEDMANN has a more oval whorl section and a 1884 Phylloceras libertum GEMMELLARO, Pl. 2, Fig. 1–5. second row of little tubercles situated near the lower part 1977 Juraphyllites libertus (GEMMELLARO). – WIEDENMAYER, Pl. 1, of the sides. Fig. 4; Pl. 3, Fig. 1, 2, 5. IEDMANN 1986 Juraphyllites libertus (GEMMELLARO). – MEISTER, Pl. 2, Fig. 8. As shown by W (1970, p. 997), these Lytocerati- 1986 Juraphyllites libertus (GEMMELLARO). – GAKOVIC, Pl. 2, Fig. 1. dae present transitional morphologies between Ectocen- 1989 Juraphyllites libertus (GEMMELLARO). – MEISTER, Pl. 2, Fig. 9. tritidae, any Tragolytoceras for ornamentation and Lytocera- 1990 Juraphyllites gr. libertus (GEMMELLARO). – DOMMERGUES & MEI- tidae mainly for the shell coiling and the whorl section. STER, Fig. 3 (15). 1993 Juraphyllites gr. libertus (GEMMELLARO). – MEISTER & BÖHM, Local range: Near the bottom of Quarry No 28 close to Pl. 3, Fig. 4. the upper ferromanganese level (adnethicus level, ? Buck- landi or ? Semicostatum zones) [Adnet quarry 28]. One clearly constricted Juraphyllites from Wetzsteingra- ben is attributed to GEMMELLARO’s species. Local range: isseli level, Margaritatus zone (Wetzstein- graben). Genus: Lytoceras SUESS 1865

Type species: Ammonites fimbriatus SOWERBY 1817.

Subgenus: Harpophylloceras SPATH 1927

Type species: Ammonites eximius HAUER 1854. Lytoceras aff. fuggeri GEYER 1893

1893 Lytoceras fuggeri GEYER, Pl. 8, Fig. 7–9. 1909 Lytoceras fuggeri GEYER. – ROSENBERG, Pl. 11, Fig. 23, 24. J. (Harpophylloceras) eximius (HAUER 1854) 1994 Lytoceras gr. fuggeri GEYER. – DOMMERGUES, FERRETTI & MEI- (Pl. 1, Fig. 10) STER, Pl. 1, Fig. 13–16. We regroup here inner moulds of Sinemurian Lytoceras. 1854 Ammonites eximius HAUER, Pl. 2, Fig. 1–4. 1977 Harpophylloceras eximius (HAUER). – WIEDENMAYER, Pl. 9, There are typical Lytoceras with rather evolute conch with Fig. 6–13 with synonymy. very weak overlapping and bearing constrictions. Orna- 1989 J. (Harpophylloceras) eximius (HAUER). – MEISTER, Pl. 3, mentation is completely missing. Thus, confusions are Fig. 1–3. possible between e.g. L. fimbriatum (SOWERBY), L. fimbriatoides Constricted Juraphyllites characterized by a keel on the (GEMMELLARO) and L. fuggeri GEYER. The specific determi- body chamber and by latero-ventral and ventral fine, pror- nation is only founded on the presence of constrictions siradiate, close ribs. which show a clearly rursiradiate orientation equivalent to Local range: Middle – Upper Carixian (Wetzsteingra- the one that characterizes the type of L. fuggeri GEYER. ben). Local range: rejectum horizon, Obtusum zone (Adnet quarry 38).

Suborder: Lytoceratina HYATT 1889 Lytoceras aff. fimbriatoides GEMMELLARO 1884 Superfamily: Lytocerataceae NEUMAYR 1875 1884 Lytoceras fimbriatoides GEMMELLARO, Pl. 3, Fig. 20–23. Family: Lytoceratidae NEUMAYR 1875 ?1909 Lytoceras sp. nov. aff. fimbriatoides GEMMELLARO. – ROSEN- Genus: Adnethiceras WIEDMANN 1970 BERG, Pl. 11, Fig. 13. ?1913 Lytoceras sp. nov. aff. fimbriatoides GEMMELLARO. – HAAS, Type species: Ammonites Adnethicus HAUER 1854. Pl. 2, Fig. 1, 2. 1942 Lytoceras fimbriatoides GEMMELLARO. – KOVÁCS, Pl. 2, Fig. 19. 1975 Lytoceras fimbriatoides GEMMELLARO. – FERRETTI, Pl. 24, Fig. 1, 2. Adnethiceras adnethicus (HAUER 1854) 1994 Lytoceras aff. fimbriatoides G EMMELLARO. – DOMMERGUES, FER- (Pl. 2, Figs. 1, 6) RETTI & MEISTER, Pl. 2, Fig. 1–4.

1854a Ammonites Adnethicus HAUER, p. 748. The constrictions and the ribs of this Lytoceras are less 1854b Ammonites Adnethicus HAUER, Pl. 1, Fig. 1–3. rursiradiate than in L. fuggeri GEYER. Moreover the ribs tend 1970 Adnethiceras adnethicus (HAUER). – WIEDMANN, Pl. 8, Fig. 1; to be clearly subdivided toward the extern part of the Text-Fig. 25 with synonymy. whorls. The considered specimen is close to the Italian 1994 Adnethiceras adnethicum (HAUER). – RAKUS, Pl. 4, Fig. 3. forms. The specimens here considered are Lytoceratids cha- Local range: Parasteroceras sp. horizon, Raricostatum racterized by strong massive spaced subradiate ribs zone (Adnet quarry 28). which cross the venter. Each rib bears a tubercle on the ventro-lateral part and between them, on the venter, the rib intensity shows little decrease. The whorl section is rounded. Genus: Derolytoceras ROSENBERG 1909 Until now four species have been described, perhaps five if we take in account (?) A. simplex (VADASZ 1908). The Type species: Ammonites lineatus tortus QUENSTEDT 1885.

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Derolytoceras sp. Fragment of a small involute Schlotheimiidae with very (Pl. 2, Figs. 2, 3) fine close ribbing. They come from the level with Arnioceras paucicostatum sensu FERRETTI no FUCINI and from the level Two small fragments of Lytoceratidae body chamber are with the Asteroceras. characterized by strong, subannular, well prominent on Local range: gr. paucicostatum horizon – rejectum horizon the ventral area, rursiradiate ribs which strongly suggest (? Semicostatum – Obtusum zones) [Adnet quarries Derolytoceras. They probably represent the microconch of 38, 41]. the co-occuring Lytoceras, here L. aff. fuggeri GEYER. Local range: rejectum horizon, Obtusum zone (Adnet quarry 38). Family: Arietitidae HYATT 1875

Suborder: Ammonitina HYATT 1889 Arietitidae ssp. Superfamily: Psilocerataceae HYATT 1867 (Pl. 3, Figs. 6, 7, 9) Family: Schlotheimiidae SPATH 1923 We have here gathered several ammonites which come Genus: Schlotheimia BAYLE 1878 from the ferromanganese level of Adnet (marmorea horizon, Late Hettangian or Early Sinemurian, quarry 31) and from Type species: Ammonites angulatus SCHLOTHEIM 1829. the base of the overlying red Limestone sequence (adnethicus level, Early Sinemurian). Some are illustrated in the Schlotheimia marmorea (OPPEL 1862) iconographical part (Pl. 3, Figs. 6, 7, 9). (Pl. 2, Figs. 4, 7–9; Pl. 3, Figs. 1, 2)

1856 Ammonites Charmassei d’ORBIGNY. – HAUER, Pl. 14, Fig. 1–3. 1862 Ammonites marmoreus OPPEL, p. 130. Subfamily: Alsatitinae HYATT 1875 1963 Schlotheimia marmorea (OPPEL). – BLIND, Pl. 2, Fig. 5. Genus: Pseudaetomoceras SPATH 1923 1963 Schlotheimia (Angulaticeras) curvata BLIND, Pl. 1, Fig. 23. 1963 Schlotheimia (Angulaticeras) harpicostata BLIND, Pl. 1, Fig. 19. Type species: Arietites abnormilobatus WÄHNER 1886. 1988 Angulaticeras marmoreum (OPPEL). – BLOOS, Pl. 1–3; Pl. 4, Fig. 7, 8; Pl. 5–8; Pl. 9, Fig. 1 with synonymy. 1990 Schlotheimia marmorea (OPPEL). – GUERIN-FRANIATTE, Pl. 18, Pseudaetomoceras abnormilobatus (WÄHNER) 1886 Fig. 3. (Pl. 3, Figs. 3, 8) BLOOS (1988, p. 6) gives an excellent description of this 1886 Arietites abnormilobatus WÄHNER, Pl. 23 (38), Fig. 4–7. species. The holotype was collected by HAUER from the ferromanganese layer (“Brandschichte“) at the base of Medium involute small sized ammonite with compres- Adnet Limestone in a quarry of Adnet area. According to sed whorl section and very sharp and high keel. The ribs BLOOS this Alpine Schlotheimiidae fauna tends to present are simple, straight and slightly rursiradiate on the flanks, earlier during the ontogeny a narrower whorl section and thicker at the ventro-lateral edge and going forward on the an acute venter than their Southwest Germany equiva- ventral part. lents. But contrarily to BLOOS we still prefer to rather attri- Local range: marmorea horizon (Angulata or Conybeari bute this species to the genus Schlotheimia than to Angulatice- zones) [Adnet quarry 31]. ras, because OPPEL’s species does not show any furrow on the venter in the pre-adult and adult stages. Only the inner whorls show a little furrow which is a paedomorphic fea- Subfamily: Arietitinae HYATT 1875 ture. Moreover for us the QUENSTEDT’s genus Angulaticeras (type species: Ammonites lacunatus BUCKMAN) includes more Genus: Paracaloceras SPATH 1923 involute and more recent forms, in other words more “deri- Type species: Ammonites coregonensis SOWERBY 1831. ved” morphologies. Our samples also are very close to the A. charmassei (d’ORBIGNY) but they have a wider, less steep, umbilicus Paracaloceras aff. grunowi (HAUER 1856) and mainly present a more rounded elliptical whorl sec- (Pl. 3, Fig. 5) tion. Local range: marmorea horizon (Angulata to Bucklandi 1856 Ammonites Grunowi HAUER, Pl. 8, Fig. 5, 6. 1879 Ammonites grunowi HAUER. – REYNES, Pl. 31, Fig. 15, 17. zones ?) [Adnet quarry 31]. 1888 Ammonites grunowi HAUER. – WÄHNER, Pl. 44, Fig. 2, 3. 1908 Arietites sp. indet aff. grunowi HAUER. – DIENER, Pl. 16, Fig. 3. 1990 Paracaloceras cf. grunowi H AUER. – TAYLOR, Pl. 1, Fig. 1, 2; Pl. 2, Genus: Angulaticeras QUENSTEDT 1883 Fig. 1. 1994 Paracaloceras grunowi HAUER. – RAKUS, Pl. 3, Fig. 3. Type species: Ammonites lacunatus BUCKMAN 1844. Evolute Arietitinae characterized by a strongly depressed whorl section and a weakly bisulcate venter with a Subgenus: Boucaulticeras SPATH 1924 wide but weak keel. The simple ribbing is gently concave Type species: Ammonites boucaultianus d’ORBIGNY 1844. and subradiate; on the venter, ribs are projected forward and fade toward the sulci. Our specimen closely agrees with WÄHNER’s illustration and can also be put near the Angulaticeras (Boucaulticeras) sp. North American specimen of TAYLOR (1990) which are a (Pl. 2, Fig. 5) little more coarsely ribbed. cf. 1990 Angulaticeras (Boucaulticeras) sp. DOMMERGUES, MEISTER & Local range: marmorea horizon (Angulata or Conybeari METTRAUX, Pl. 2, Fig. 1. zones) [Adnet quarry 31].

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Genus: Coroniceras HYATT 1867 Arnioceras rejectum FUCINI 1902 (Pl. 3, Figs. 12, 14–16; Pl. 4, Fig. 2–4) Type species: Ammonites kridion ZIETEN 1830 (ICZN opi- nion 324). 1902 Arnioceras rejectum FUCINI, Pl. 17, Fig. 14; Pl. 19, Fig. 1–6. 1993 Arnioceras gr. ceratitoides (QUENSTEDT). – MEISTER & BÖHM, Pl. 4, Fig. 3, 5, 6, 10. Coroniceras cf. lyra HYAT T 1889 1994 Arnioceras rejectum F UCINI. – DOMMERGUES, FERRETTI & MEISTER (Pl. 3, Fig. 13) Pl. 2, Fig. 13–17.

1879 Ammonites multicostatus S OWERBY. – REYNES, Pl. 24, Fig. 21–22 These ammonites form the second acme of Arnioceras only. and they are associated with Asteroceras. They also show a 1889 Coroniceras lyra HYAT T , Pl. 4, Fig. 6–7; Pl. 5, Fig. 1–3. large variability and the morphological differences, essen- Coroniceras lyra YAT T 1889 H var. A, Pl. 4, Fig. 1, 8, 12–14. tially in rib density, with the underlying A. gr. paucicostatum 1889 Coroniceras lyra HYAT T var. B, Pl. 4, Fig. 2–5. 1889 Coroniceras lyra HYAT T var. C, Pl. 4, Fig. 9–11, 15, 16. sensu FERRETTI are little. Indeed A. rejectum FUCINI presents 1966 Coroniceras lyra HYAT T . – GUERIN-FRANIATTE, Pl. 22; Pl. 25; globally a closer ribbing. New data from the Apennines Pl. 26, Fig. 1–3; Pl. 27; Pl. 28. (DOMMERGUES et al., 1994) carry out to attribute these Ad- 1984 Coroniceras lyra HYAT T . – CORNA, Pl. 7, Fig. 1. net forms, previously attributed to A. ceratitoides (QUEN- 1989 Coroniceras aff. lyra HYAT T . – MEISTER & LOUP, Pl. 2, Fig. 7; STEDT), to A. rejectum FUCINI (MEISTER & BÖHM, 1993). In Pl. 3, Fig. 2; Pl. 4, Fig. 2. some samples, the smooth juvenile stage can reach 8 mm It is only a fragment of an evolute phragmocone charac- of diameter. terized by a thick subtrapezoidal whorl section as broad as Local range: rejectum horizon, Obtusum zone (Adnet high, subradiate strong ribs bearing unconspicuous quarry 38). latero-ventral tubercles, less convex and nearly tricarinate venter with two large but shallow sulci. From the tubercles and toward the lateral keels, ribs are attenuated and weakly projected forward. This feature carries out to put the PATH considered ammonite near late Coroniceras of the Semicos- Subfamily: Asteroceratinae S 1946 tatum zone like Coroniceras lyra H YAT T rather than to old Coro- Genus: Caenisites BUCKMAN 1925 niceras of the Bucklandi zone. Type species: Caenisites caeneus BUCKMAN 1925. Local range: cf. lyra level, Semicostatum zone (Adnet quarry 28). Caenisites sp.

We bring near to BUCKMAN’s genus a rather involute (U/D Genus: Arnioceras HYATT 1867 = 0,33) and large Asteroceratinae (D = 350 mm). It is Type species: Arnioceras cuneiforme HYAT T , 1867. characterized by a wide tricarinate-bisulcate venter, still well developed on the body chamber. The ribs are strong, Arnioceras gr. paucicostum sensu FERRETTI 1975 spaced and subradiate; on the body chamber they disap- pear at the middle of the flank and the extern part be- non FUCINI 1902 comes smooth; only the tricarinate venter persists. (Pl. 3, Fig. 11; Pl. 4, Figs. 1, 5) This ammonite cannot be brought near any nowadays non 1901–05 Arnioceras ceratitoides var. paucicosta FUCINI, Pl. 18, known Caenisites. Only C. brooki (SOWERBY) presents a similar Fig. 9, 10, 12–14. umbilicus which is the narrowest for the genus, but the 1975 Arnioceras ceratoides paucicosta FUCINI. – FERRETTI, ornamentation is very different and the whorl section of Pl. 22, Fig. 1–3. the alpine ammonite is more compressed than in SOWER- 1993 Arnioceras gr. mendax var. rariplicatum FUCINI. – MEISTER & BÖHM, Pl. 4, Fig. 4. BY’s species (Text-Fig. 12). 1994 Arnioceras gr. paucicosta sensu FERRETTI non FUCINI. – By comparison Eparietites shows a clearly narrower umbi- DOMMERGUES, FERRETTI & MEISTER Pl. 2, Fig. 9–12. licus and the whorl section is more compressed and tri- ? 1994 Arnioceras gr. ceratitoides (QUENSTEDT). – RAKUS, Pl. 5, angular with a Fig. 1. fastigate venter These forms constitute the first acme of the Arnioceras in because of the the studied area. Following DOMMERGUES et al. (1994), we disappearance of regroup in A. gr. paucicostatum sensu FERRETTI these Ar- the sulci. nioceras which present a great intraspecific variability in rib Local range: density and in whorl-section and which can attain a rela- Caenisites sp. le- tively large size (D = 120 mm). Ribs are rather acute and vel, Turneri zone rigid and juvenile smooth stage quite short. In the Adnet (Adnet). area, these Arnioceras are characterized by a low rib density and thus are very close to the Subbriançonnais Arnioceras: A. cf. mendax var. rariplicata FUCINI sensu DOMMERGUES et al. (1990). This latter FUCINI’s name was previously used to gather Austrian ammonites (MEISTER & BÖHM, 1993). But as assumed by DOMMERGUES et al. (1994) almost all the Arnioceras described in FUCINI (1901–1905), more than 25 species or varieties, are coming from 2 beds of the Monte di Cetona and must be regrouped in only one species with Text-Fig. 12. a large variability. Caenisites sp. whorl Local range: gr. paucicostatum horizon, ? Semicostatum – section. Obtusum zones (Adnet quarry 41, Glasenbach). Scale = 10 cm.

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Genus: Asteroceras HYATT 1867 (SCHLATTER, 1984). The simplicity of the morphological characters in this ammonite and mainly the simple sutu- Type species: Ammonites stellaris SOWERBY, 1815. re line make difficult a definitive position.

Asteroceras gr. retusum (REYNES) sensu SACCHI-VIALLI & CANTALUPPI 1961 Epophioceras deciduum (HYAT T 1867) non REYNES 1879 (Pl. 6, Figs. 1, 3) (Pl. 4, Figs. 6–10; Pl. 5, Figs. 1–10) 1856 Ammonites nodotianus d’ORBIGNY. – HAUER, Pl. 6, Fig. 1–3. 1961 Asteroceras retusum REYNES. – SACCHI-VIALLI & CANTALUPPI, 1867 Ophioceras deciduum HYAT T , p. 76 (new name for the prece- Pl. 4, Fig. 1–4. ding). ?1961 Asteroceras confusum SPATH. – SACCHI-VIALLI & CANTALUPPI, 1925 Pleurechioceras deciduum (HYAT T ). – TRUEMAN & WILLIAMS, p. Pl. 4, Fig. 5. 719. 1993 Asteroceras aff. confusum SPATH. – MEISTER & BÖHM, Pl. 4, 1958 Echioceras cf. deciduum (HYAT T ). – DONOVAN, p. 17, Text-Fig. 3 Fig. 7, 9, 11. with synonymy. 1973 Echioceras deciduum (HYAT T ). – GETTY, Pl. 3, Fig. 2. Evolute Asteroceras characterized by a subrectangular whorl-section with a large nearly tricarinate ventral area The generic attribution of O. deciduum HYAT T remains ten- bearing well developed and broad sulci and a prominent tative. Although our samples agree with HYAT T ’s species, and narrow keel. Moreover the transition between sides two genera are proposed in the recent literature: Epophioce- and the sulci is very steep. The sides are slightly convex ras or Echioceras. The evolute coiling shell, the prorsiradiate and subparallel. The ribs are prorsiradiate and conspicu- ribbing, the sustained subcircular whorl section, slightly ous until the ventro-lateral part, even at the adult stage. A. higher than thick (Text-Fig. 3 in DONOVAN, 1958), the quite margaritatoides S PATH is a close species, as shown in SPATH’s large groove on both sides of the keel characterize the first type (1926, Pl. 10, Fig. 5) but, at least in the inner whorls, genus. With Echioceras deciduum (HYAT T ) shares very coarse the rib density is higher. The ventro-lateral edge is more and distant ribs. Even in the diagramm of GETTY (1973, convergent toward the venter and the transition is less ab- Fig. 3) about the Echioceratidae, E. deciduum (HYAT T ) occu- rupt. By comparison with the Saltrio fauna, our samples pies an marginal position which underlines the originality present, on the whole, a more compressed whorl-section of this species. and the sulci and keel seem slightly crenulated. In the present paper, we follow the classic systematic In Asteroceras varians FUCINI, the ornamentation disap- position (DONOVAN et al., 1981) and we attribute E. deciduum pears near the extern part and the ventral area is narrower. (HYAT T ) to the genus Epophioceras mainly to take in account The sulci are less developed (CECCA et al., 1987) and the the rib ontogeny. Indeed the ribs are relatively close in the umbilicus smaller. inner whorl and they become progressively distant during The numerous well preserved Asteroceras from Adnet the ontogeny. Whereas in the Echioceras this changing is show a great homogeneity in their morphology and allow more sudden. us to regroup the major part of the Asteroceras from Breiten- By comparison E. landrioti (d’ORBIGNY) has a less promi- berg and Schmiedwirt under the specific name A. gr. retu- nent keel, closer and less prorsiradiate ribs. The whorl sum (REYNES) sensu SACCHI-VIALLI & CANTALUPPI. section is broader. E. longicella (QUENSTEDT) presents closer Local range: rejectum horizon, Obtusum zone (Adnet ribs and a broader whorl section too. quarry 38). A. margaritatoides SPATH and probably A. retusum Local range: Obtusum zone (Adnet quarry 28 and Mu- (REYNES) sensu SACCHI-VIALLI & CANTALUPPI indicate the seum of Adnet). lower part of Stellare subzone (DOMMERGUES et al., 1994). Genus: Eparietites SPATH 1924 ARONA Asteroceras aff. saltriensis (P 1896) Type species: Arietites tenellus SIMPSON in BUCKMAN (Pl. 5, Fig. 11) 1912. 1896 Arietites saltriensis PARONA, Pl. 8, Fig. 2, 3. 1903 Asteroceras saltriensis (PARONA). – FUCINI, Pl. 33, Fig. 4–6. Eparietites glaber GUERIN-FRANIATTE 1966 ?1994 Asteroceras obtusum (SOWERBY). – RAKUS, Pl. 5, Fig. 3. (Pl. 7, Fig. 1) The specimen collected ex situ, shows a clearly “derived” morphology charaterized by the disappearance of 1966 Eparietites glaber GUERIN-FRANIATTE, Pl. 198, Fig. 1, 2. 1990 Eparietites aff. glaber GUERIN-FRANIATTE. – DOMMERGUES, MEI- the sulci, replaced by two flat and smooth slopes on both STER & METTRAUX, Pl. 198, Fig. 1, 2. sides of the keel. The ribs are strong, slightly arched, going The specimen here considered is characterized by a ra- forward on the ventro-lateral edge. “A.” blakei SPATH is a close form still more “derived” where the ribbing cross ther short juvenile ornamented stage and a rather subfa- over the venter in the adult morphology. This type of mor- stigate ventral area with two still well developed flat phology already suggests the genus Aegasteroceras. bands. In our specimen (D = 85 mm) the rather close ribbed stage seems to end at about 30 mm (alteration ?). Local range: aff. saltriensis level, Obtusum zone. Such The holotype (GUERIN-FRANIATTE, 1966) shows a longer or- forms indicate the middle to upper Stellare subzone namented stage. In E. undaries (QUENSTEDT), it is still longer. (Adnet quarry 28). The “subbriançonnais” population (DOMMERGUES et al., 1990) presents a more acute (less shouldered) ventral part; the flat bands are less deep and always more oblique Genus: Epophioceras SPATH 1924 and the oxycone morphology is clearly expressed. E. colle- Type species: Ammonites landrioti d’ORBIGNY, 1850. noti (d’ORBIGNY) is an extreme form toward the oxycone Remark: The systematic position of the genus Epophioce- morphology and the loss of the ornamentation. ras is still in discussion: Asteroceratid or Echioceratid Local range: Obtusum zone (Museum of Adnet).

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Genus: Parasteroceras DOMMERGUES, FAURE This suboxycone Oxynoticeras presents rather coarse & PEYBERNES 1986 spaced arched forward ribs with slightly prorsiradiate pri- maries on the sides, and intercalatories close to the ven- Type species: Parasteroceras rakusi DOMMERGUES, FAURE ter. It bears a characteristic pinched keel. This morpholo- & PEYBERNES 1986. gical features well agree with the diagnosis of O. oxynotum (QUENSTEDT). O. polyophyllum (SIMPSON), a close species, bears a coarser ornamentation. Parasteroceras sp. oxynotum (Pl. 6, Fig. 2; Pl. 7, Fig. 2; Pl. 8, Fig. 1) Local range: level, Oxynotum zone (Museum of Adnet). For the genus Parasteroceras our specimens are compressed and very oxycone. But if the venter is acute, the umbilicus is rather open. The steep umbilical wall is bor- Oxynoticeras aff. soemanni (DUMORTIER 1867) dered by an angular umbilical edge. (Pl. 7, Figs. 3, 4) Although the ornamentation is unconspicuous because of alteration, the lateral ribs are present and persist until 1867 Ammonites soemanni DUMORTIER, Pl. 40, Fig. 2–4; Pl. 43, the middle part of the flanks. The suture line seems to be Fig. 1, 2. 1879 Oxynoticeras soemanni (DUMORTIER). – REYNES, Pl. 45, rather simple (Text-Fig. 13). Such features (DOMMERGUES Fig. 44–46. et al., 1986, in press) are characteristic of the genus Para- 1901 Oxynoticeras soemanni (DUMORTIER). – FUCINI, Pl. 1, steroceras. Fig. 1. 1914 Oxynoticeras soemanni (DUMORTIER). – PIA, Pl. 6, Fig. 25; Pl. 10, Fig. 4. ?non 1991 Oxynoticeras soemanni (DUMORTIER). – COPE, Pl. 4, Fig. 4. Very oxycone and smooth specimens the morphology of which can suggest Radstockiceras. Nevertheless in the adult morphology the whorl section becomes more rounded and broader in the lower 1/3 of the sides, features which are characteristic of the genus Oxynoticeras. The suture line is quite simple (Text-Fig. 14).

Text-Fig. 13. Text-Fig. 14. Parasteroceras sp. suture line. Oxynoticeras aff. soemanni (DUMORTIER) suture line.

As in FUCINI (1905, Pl. 1, Fig. 5), the body chamber is Local range: Parasteroceras sp. horizon, Raricostatum very extra-umbilicate. zone (Adnet quarry 28). By comparison with the two species nowadays known P. pulchellum FUCINI and P. rakusi DOMMERGUES, FAURE & PEY- BERNES, the ventral area is thinner. Genus: Gleviceras BUCKMAN 1918 Local range: Parasteroceras sp. horizon, Raricostatum Type species: Gleviceras glevense BUCKMAN 1918. zone (Adnet quarry 28). Remark: Two main types of morphology can be recogni- zed among the Gleviceras collected in the Adnet area. They specially differ by the periumbilical edge which is Family: Oxynoticeratidae HYATT 1875 more or less angular and by the ventral part which is Genus: Oxynoticeras HYATT 1875 shouldered or compressed.

Type species: Ammonites oxynotus QUENSTEDT 1845. Gleviceras doris (REYNES) sensu PIA 1914 (Pl. 9, Fig. 1) Oxynoticeras gr. oxynotum (QUENSTEDT 1845) (Pl. 9, Fig. 2) no 1879 Ammonites doris REYNES, Pl. 41, Fig. 13–15. 1914 Oxynoticeras doris (REYNES). – PIA, Pl. 1, Fig. 1; Pl. 6, Fig. 1; 1845 Ammonites oxynotus QUENSTEDT, Pl. 5, Fig. 11. Pl. 8, Fig. 1. 1956 Oxynoticeras oxynotum (QUENSTEDT). – SÖLL, Pl. 17, Fig. 1–10; ? 1987 Gleviceras aff. doris (REYNES). – CECCA, DOMMERGUES, MOU- Pl. 18, Fig. 1. TERDE & PALLINI, Pl. 2, Fig. 1. 1961 Oxynoticeras oxynotum (QUENSTEDT). – DEAN, DONOVAN & HO- WARTH, Pl. 66, Fig. 5; Pl. 67, Fig. 3. Gleviceras is characterized by rather coarse ribs, by a 1984 Oxynoticeras oxynotum (QUENSTEDT). – CORNA, Pl. 11, Fig. 5. large whorl section and by a shouldered ventral area. 1985 Oxynoticeras oxynotum (QUENSTEDT). – COMAS RENGIFO, Pl. 2, Moreover the periumbilical area is abruptly rounded and Fig. 6 with synonymy. the umbilical wall is large (see PIA, Pl. 8, Fig. 1). G. boucaul- 1990 Oxynoticeras oxynotum (QUENSTEDT). – HOLLINGWORTH, Pl. 1, Fig. 7–9. tianum (DUMORTIER) sensu PIA shows great affinities but the 1993 Oxynoticeras oxynotum (QUENSTEDT). – DOMMERGUES, Pl. 4, more compressed whorl section is not so clearly shoul- Fig. 5. dered.

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G. greenoughi (SOWERBY) in PARONA (1896, Pl. 1, Fig. 2) 1993 Microderoceras aff. gigas (QUENSTEDT). – MEISTER & BÖHM, Pl. 3 presents a more finely ribbing and its periumbilical area is Fig. 3. not so abruptly rounded (less angular). This large evolute ammonite (D = 300–350 mm) shows a Local range: Parasteroceras sp. horizon, Raricostatum spaced coarse and bituberculate ribbing. This ornamen- zone (Adnet quarry 28). tation persists until the adult body chamber. Microderoceras aff. gigas (QUENSTEDT) co-occurs with Gleviceras greenoughi (SOWERBY sensu HAUER). Gleviceras greenoughi (SOWERBY) Local range: Coming from one isolated bed from the sensu HAUER 1856 quarry (No 12), their exact biostratigraphical position (Pl. 9, Fig. 3) cannot be precised. At the present time Gleviceras is not known before the Oxynotum zone; this suggests an age 1856 Ammonites greenoughi SOWERBY. – HAUER, Pl. 12, Fig. 1–5. aff. 1860 Ammonites greenoughi SOWERBY. – OOSTER, Pl. 16, Fig. among Oxynotum and Raricostatum zones (aff. gigas 1, 2. level) [Adnet quarry 12]. 1914 Oxynoticeras greenoughi sensu (HAUER non SOWERBY). – PIA, Pl. 7, Fig. 30; Pl. 8, Fig. 5. aff. 1958 Oxynoticeras (Gleviceras) aff. doris (REYNES non SOWERBY). – Family: Coeloceratidae HAUG 1910 DONOVAN, Text-Fig. 1 b, c. Genus: Miltoceras WIEDENMAYER 1980 This Gleviceras shows a subelliptical rather compressed Type species: Aegoceras sellae GEMMELLARO 1884. whorl section and rather coarse spaced and sinuous lateral ribs. The periumbilical area is smoothly rounded, oblique without angle, moreover the umbilicus is less Miltoceras (?) sp. deep than in Gleviceras doris (REYNES sensu PIA). In G. subgui- (Pl. 3, Fig. 10) balianum P IA also collected in the Adnet area, the rib density 1993 A. (Miltoceras) juv. – MEISTER & BÖHM, Pl. 4, Fig. 12. is finer and closer, ribs are less sinuous, the section is more compressed. Besides G. victoris (DUMORTIER) presen- We bring near to the genus Miltoceras a fragment of an ts narrower whorl section and finer, closer ribbing. evolute ammonite characterized by a subrounded whorl A large specimen (D = 300 mm) shows a more rigid and section, high latero-ventral row of small tubercles, rather closer ribbing and the ventral part perhaps is a little more close lateral ribbing and ventral secondary ribs. It is very shouldered until the adult stage. But the variability and close to the specimen illustrated by MEISTER & BÖHM ontogenetic development of these Gleviceras from the Ad- (1993, Pl. 4, Fig. 12). net area is not well understood. Local range: rejectum horizon, Obtusum zone (Adnet Local range: aff. gigas level, ? Oxynotum – Raricos- quarry 38). tatum zone (Adnet quarry 12). Family: Liparoceratidae HYATT 1867 Genus: Paramicroderoceras DOMMERGUES, Family: Echioceratidae BUCKMAN 1913 FERRETTI & MEISTER 1994 Genus: Tmaegophioceras SPATH 1925 Type species: Microderoceras birchioides ROSENBERG Type species: Arietites laevis GEYER 1886. 1909.

Tmaegophioceras laeve (GEYER 1886) Paramicroderoceras sp. (Pl. 8, Fig. 3) (Pl. 8, Fig. 4) 1886 Arietites laevis STUR. – GEYER, Pl. 3, Fig. 10. These specimens well correspond to the diagnosis of 1984 Tmaegophioceras laeve (GEYER). – GECZY & SCHLATTER, p. 95, Abb. 3. the genus Paramicroderoceras (DOMMERGUES et al., 1994). They are subplaticone-evolute ammonites bearing a Very rare serpenticone ammonite with a subquadrate complex ornamentation. Rather unconspicuous primary depressed whorl section, flat keeled venter bordered by bituberculated ribs support clear secondary striae which two rather large sulci. In this taxon the ornamentation is are present during almost the entire ontogeny (DOM- unconspicuous and if it exists, reduced to spaced smooth MERGUES et al., 1994) as well on the sides as on the ventral undulations. part. Local range: Probably upper part of Obtusum zone (see The specific distinction is more complex specially be- GECZY & SCHLATTER, 1984) [Adnet quarry 41]. cause of the scarcity of the material. The whorl expansion rate of the Adnet specimens seems to be moderate in the first whorls (until 70–80 mm of dia- Superfamily: Eoderocerataceae SPATH 1929 meter) but slightly increases in the intermediate whorls (near 120 mm of diameter). Our specimens show affinities Family: Eoderoceratidae SPATH 1929 with P. birchiades (ROSENBERG) and with P. nothum (MENEGHINI Genus: Microderoceras HYATT 1871 in FUCINI). Nevertheless P. birchiades (ROSENBERG) has finer Type species: Ammonites birchi SOWERBY 1820. and closer secondary ribbing and in P. nothum (MENEGHINI in FUCINI) the primary ornamentation is more developped on the ventral part. The other morphologies regrouped in P. Microderoceras aff. gigas (QUENSTEDT, 1883) sp. A and P. sp. B by CECCA et al. (1987) and DOMMERGUES (Pl. 8, Fig. 2) et al. (1994) differ by their higher whorl section, with more 1882/85 Ammonites birchii gigas QUENSTEDT, Pl. 18, Fig. 13. attenuated ornamentation in P. sp. A and well developed 1928 Microderoceras gigas (QUENSTEDT) – BUCKMAN, Pl. 762. lateral primary ribbing for P. sp. B.

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Local range: Parasteroceras sp. horizon, Raricostatum Local range: algovianum level, Margaritatus zone (Wetz- zone (Adnet quarry 28). steingraben).

Genus: Androgynoceras HYATT 1867 Superfamily: Hildocerataceae HYATT 1867 Family: Hildoceratidae HYATT 1867 Type species: Ammonites hybrida d’ORBIGNY 1844. Subfamily: Harpoceratinae NEUMAYR 1875 Genus: Protogrammoceras SPATH 1913 Androgynoceras gr. geyeri (SPATH 1938) (Pl. 9, Fig. 4) Type species: Grammoceras bassanii FUCINI 1900.

*1938 Liparoceras geyeri SPATH, Pl. 4, Figs. 4, 6; Pl. 6, Fig. 2; Pl. 10, Figs. 3. 4; Pl. 18, Fig. 11. Protogrammoceras gr. isseli (FUCINI 1900) 1990 “Androgynoceras” geyeri (SPATH). – DOMMERGUES, MEISTER & METTRAUX, Pl. 5, Fig. 12; with synonymy. (Pl. 9, Fig. 6; Pl. 10, Figs. 4, 8) 1991 Androgynoceras gr. geyeri (SPATH). – BLAU & MEISTER, Pl. 5, Fig. 3–5. 1900 Grammoceras isseli FUCINI, Pl. 9, Fig. 6–8. 1983 Fuciniceras isseli (FUCINI). – BRAGA, Pl. 2, Fig. 10; Pl. 3, Small sized dimorphic ammonite characterized by a Fig. 1–5. juvenile “capricorne” stage followed by a “Liparoceras” adult 1983 Protogrammoceras isseli (FUCINI). – DOMMERGUES, FERRETTI, one. In our specimen, the short “capricorne” Beaniceras like GECZY & MOUTERDE, Pl. 4, Fig. 1–12. 1991 Protogrammoceras gr. isseli (FUCINI). – BLAU & MEISTER, Pl. 5, stage suggests the A. geyeri (SPATH) group rather than A. Figs. 15–22. hybrida (d’ORBIGNY) or A. subhybrida (SPATH) which are quite 1993 Protogrammoceras cf. isseli (FUCINI). – MEISTER & BÖHM, Pl. 8, larger sized ammonites. Figs. 11, 14. Local range: geyeri level, Ibex zone (Wetzsteingraben). Protogrammoceras with falcate, fine and close ribs. Toward the end of the growth the rib density increases and the ventral area becomes more rounded. Family: Amaltheidae HYATT 1867 Local range: isseli level, Margaritatus zone (Wetzstein- graben). Genus: Amaltheus DE MONTFORT 1808

Type species: Amaltheus margaritatus DE MONTFORT 1808. Subgenus: Paltarpites BUCKMAN 1922 Amaltheus stokesi (SOWERBY 1818) (Pl. 10, Fig. 1) Type species: Paltarpites paltus BUCKMAN 1922.

*1818 Ammonites Stokesi MONTFORT, Pl. 190. 1958 Amaltheus stokesi (MONTFORT). – HOWARTH, Pl. 1, Figs. 5, 7, P. (Paltarpites) sp. 12–14; Pl. 2, Figs. 1, 3, 10; Text-Figs. 4, 5; with synonymy. We attribute to this subgenus two fragments of body 1986 Amaltheus stokesi (MONTFORT). – MEISTER, Pl. 19, Fig. 2; chamber of quite large involute Protogrammoceras charac- Pl. 20, Figs. 1, 8; with synonymy. terized by a high compressed whorl section bearing an 1991 Amaltheus stokesi (SOWERBY). – BLAU & MEISTER, Pl. 5, Fig. 9 with synonymy. acute fine keel and showing falcate, very fine and close 1993 Amaltheus (Amaltheus) stokesi (SOWERBY). – Pl. 1, Fig. 7. ribs. P. (P.) meneghini (BONARELLI) is a closer ribbed taxon and Classical Amaltheus species for the lower part of the conversely P. (P.) ilurcense BRAGA displays coarser and more Domerian in the Euroboreal realm, A. stokesi (SOWERBY) is spaced ribs. characterized by a slightly sigmoid lateral ribbing and by a crenulate keel which remains connected with ribs. Local range: algovianum level, Margaritatus zone (Wetz- steingraben). Local range: isseli level, Margaritatus zone (Wetzstein- graben).

Amaltheus margaritatus DE MONTFORT 1808 Subfamily: Arieticeratinae HOWARTH 1955 (Pl. 9, Fig. 5) Genus: Arieticeras SEGUENZA 1885

*1808 Amaltheus margaritatus DE MONTFORT, p. 91, Fig. 90. Type species: Ammonites algovianus OPPEL 1862. 1958 Amaltheus margaritatus DE MONTFORT. – HOWARTH, Pl. 3, Figs. 4–6; Text-Figs. 8, 9; with synonymy. 1986 Amaltheus margaritatus DE M ONTFORT. – MEISTER, Pl. 20, Fig. 9; Arieticeras gr. algovianum (OPPEL 1862) Pl. 22, Fig. 1; Pl. 23, Fig. 6; with synonymy. (Pl. 10, Figs. 2, 3, 5–7) 1988 Amaltheus margaritatus DE MONTFORT. – MEISTER, Pl. 1, Figs. 2–4; Pl. 2, Figs. 1–3, 5; Pl. 3, Figs. 3–5, 10; Pl. 4, 1862 Ammonites Algovianum OPPEL, p. 137. Figs. 1, 3, 4. 1988 Arieticeras cf. algovianum – SMITH, TIPPER, TAYLOR & GUEX, 1991 Amaltheus margaritatus DE MONTFORT. – BLAU & MEISTER, Pl. 5, Pl. 4, Fig. 10, 11. Fig. 10. 1989 Arieticeras gr. algovianum (OPPEL). – MEISTER, Pl. 7, Fig. 10–12 These and poorly preserved specimens come from the with synonymy. 1991 Arieticeras gr. algovianum (OPPEL). – BLAU & MEISTER, Pl. 6, A. gr. algovianum (OPPEL) levels. They are typical Amaltheus Fig. 23; Pl. 7, Fig. 1–18. characterized by clearly disconnected ribs and a crenu- 1993 Arieticeras gr. algovianum (OPPEL). – MEISTER & BÖHM, Pl. 9, lated keel. Moreover the crenulation of the keel is not as Fig. 5, 7–10. coarse as in A. stokesi (SOWERBY). 1993 Arieticeras ex. gr. algovianum (OPPEL). – JAKSCH, Pl. 2, Fig. 1.

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These forms belong to a faunal set already described EARLY SINEMURIAN from the Lienz Dolomites (BLAU & MEISTER, 1991), from the Our data from the Early Sinemurian are rare and the ma- Salzburg area and Rötelstein (MEISTER & BÖHM, 1993). jor part of the material was collected ex situ. If it is in situ, Local range: algovianum level, Margaritatus zone (Wetz- the places of collect are too much isolated to propose any steingraben). local correlations. Nevertheless all specimens come from the lower part of the Adnet Limestones sequence not far from the bottom of the quarries. By comparison with the Genus: Leptaleoceras BUCKMAN 1918 sequences of well studied areas like the southern Jura (CORNA, 1985, 1987), we can suspect that our material Type species: Leptaleoceras leptum BUCKMAN 1918. comes from several levels: adnethicus level Leptaleoceras aff. accuratum (FUCINI 1931) A level, slightly above the suspected condensed mar- (Pl. 10, Figs. 9–11) morea horizon, contains Adnethiceras adnethicus, some Arietiti- dae sp. and Arnioceras (?) sp. Its age is to place in an interval 1931 Arieticeras (?) accuratum FUCINI , Pl. 8, Fig. 7, 8. including the Bucklandi zone and the Semicostatum one. non 1952 Arieticeras accuratum FUCINI. – VENZO, Pl. A, Fig. 8, 9. 1968 Arieticeras accuratum FUCINI. – CANTALUPPI & BRAMBILLA, cf. lyra level Pl. 27, Fig. 1. 1977 Ugdulunia accurata (FUCINI). – FANTINI SESTINI, Pl. 37, A Coroniceras cf. lyra, ex situ, also suggests the lower part Fig. 7; Pl. 38, Fig. 7, 8; Pl. 39, Fig. 1–9. of Semicostatum zone (Charlesi subzone) 1980 Arieticeras accuratum FUCINI. – WIEDENMAYER, Pl. 17, Fig. 15–18. Caenisites sp. level 1982 Leptaleoceras accuratum (FUCINI). – BRAGA, COMAS RENGI- The presence of Caenisites sp. and Arnioceras sp., in an ex FO, GOY & RIVAS, Pl. 3, Fig. 1. 1983 Leptaleoceras accuratum (FUCINI). – BRAGA, Pl. 12, situ assemblage, attests the presence of the Turneri Fig. 3–10. zone. ? 1983 Leptaleoceras accuratum (FUCINI) preaccuratum BRAGA, Pl. 11, Fig. 27–30; Pl. 12, Fig. 1, 2. gr. paucicostum horizon 1985 Arieticeras accuratum FUCINI. – COMAS RENGIFO, Pl. 16, The Arnioceras gr. paucicostum horizon is characterized by Fig. 1, 2. the index species, Phylloceras cylindricum, Juraphyllites sp., An- ? 1988 Leptaleoceras aff. accuratum (FUCINI). – SMITH, TIPPER, TAY- LOR & GUEX, Pl. 4, Fig. 9. gulaticeras (Boucaulticeras) sp. This faunal event is well represented throughout the Salzburg area and was previ- The Arieticeratinae co-occur with Arieticeras gr. algovianum ously described in the Schmiedwirt locality by MEISTER & (OPPEL). They are evolute compressed forms with a narrow BÖHM (1993) as mendax horizon. It can also be correlated ventral area bearing a keel but without sulci. The rather with the Arnioceras sp. level from Breitenberg (MEISTER & evanescent ornamentation is rather rigid. The ribbing is BÖHM, 1993). Because of the long range of Arnioceras spe- less sinuous and the umbilicus more opened than in “A.” cies, it is difficult to precise an age but one can suggest a ugdulenai (GEMMELLARO). period between the Semicostatum zone and the lower part Local range: algovianum level, Margaritatus zone (Wetz- of Obtusum zone. The problem is similar for the Central steingraben). Apennine succession (DOMMERGUES et al., 1994). In that case, Arnioceras gr. paucicostum is associated with “Ectocen- trites” altiformis BONARELLI, Bouhamidoceras sp. and “Mi- 5. Biostratigraphical Framework croderoceras” cf. olenoptychum (FUCINI) (Text-Fig. 16). For the use of the terms “horizon” or “level“, we refer to MEISTER et al. (1994, p. 141). LATE SINEMURIAN Obtusum Zone LATE HETTANGIAN to EARLY SINEMURIAN Stellare subzone Angulata Zone to Bucklandi Zone gr. retusum horizon Complanata subzone to Conybeari subzone This horizon which is characterized by the association of Asteroceras retusum sensu SACCHI-VIALLI & CANTALUPPI, Ar- marmorea horizon nioceras rejectum, Angulaticeras (Boucaulticeras) sp., Phylloceras cy- A ferromanganese level forms the base of the red Adnet lindricum, Ph. (Calliphylloceras) bicicolae, Ph. (Zetoceras) sp., Part- Limestones in the quarries of Adnet. A biostratigraphical schiceras gr. striatocostatum (from Glasenbach). Miltoceras (?) condensation of this ammonite rich level is possible, but sp., Derolytoceras sp., Lytoceras aff. fuggeri and Juraphyllites sp. cannot be demonstrated by the analysis of our material. Asteroceras retusum, clearly indicates the Stellare subzone, The ammonite assemblage includes Schlotheimia marmorea, probably the lower or middle part of this biochronologic Phylloceras sp., Juraphyllitidae sp., Pseudaetomoceras abnormi- unit. lobatus, Paracaloceras aff. grunowi, Paracaloceras sp., Arietitidae ssp. (Text-Fig. 15). This association and the stratigraphi- aff. saltriensis level cal context cannot clearly indicate a precise age which (called stellare level in MEISTER & BÖHM, 1993). still imposes some discussion (GUEX & TAYLOR, 1976; We have collected ex situ Asteroceras aff. saltriensis, a spe- BLOOS, 1983, 1988; TAYLOR, 1986, 1990). If Schlotheimia mar- cies which seems to indicate the upper part of the Stellare morea seems to indicate a Late Hettangian age (BLOOS, subzone. Indeed its morphology is already close to that of 1988, p. 74) the other associated taxa are Arietids and the genus Aegasteroceras from the top of the Stellare sub- suggest the Early Sinemurian (TAYLOR, 1986, 1990). zone.

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Text-Fig. 15. Biostratigraphical framework of the studied areas.

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Text-Fig. 16. Biostratigraphical comparisons and correlations between NW Europe, Middle Austroalpine, Upper Austroalpine and Apennines.

The two latter assemblages can be roughly correlated viceras begins from the Oxynotum zone and includes the with the Asteroceras sp. horizon from the Middle Austroal- Raricostatum zone meanwhile the distribution of Mi- pine (DOMMERGUES & MEISTER, 1990) and with the rejectum croderoceras aff. gigas is restricted to the Turneri zone. horizon from the Central Apennine (DOMMERGUES et al., 1994). Nevertheless in Italy, the interval of doubt for its zonal or subzonal attribution is still wider. Raricostatum Zone Coming probably from the Obtusum zone Epophioceras de- Densinodulum and Raricostatum subzones ciduum and Tmaegophioceras laeve also indicate the Stellare subzone or perhaps the base of the Denotatus one (GECZY Parasteroceras sp. horizon & SCHLATTER, 1984). By comparison with the Central Apennines (DOM- MERGUES et al., 1994) we attribute with doubt the Paras- Denotatus subzone teroceras sp. horizon to the lower-middle part of the Rari- costatum zone. The fauna is characterized by Parasteroceras glaber level sp., Paramicroderoceras sp., Oxynoticeras aff. soemanni, Gleviceras An ex situ specimen of E. glaber suggests the upper part doris sensu PIA, Phylloceras cylindricum, Juraphyllites nardii. of the Denotatus subzone. A Lytoceras aff. fimbriatoides collected about 40 cm below this horizon, can also be attributed to the Raricostatum Oxynotum Zone zone. In the Central Apennine, two Parasteroceras assemblages Oxynotum subzone can be proposed; but the faunal associations which are gr. oxynotum level different from the alpine ones, do not allow precise correlations. Only one O. gr. oxynotum, also ex situ, allows us to attest the presence of the Oxynotum subzone on the Adnet area. Tentative correlations can be proposed with the Middle PLIENSBACHIAN Austroalpine where an episode with Oxynoticeras is described. CARIXIAN SUBSTAGE All the Pliensbachian taxa described here are coming aff. gigas level from Wetzsteingraben. This Liassic outcrop is a distorted The assemblage including Microderoceras aff. gigas and olistolith and no precise biostratigraphy is possible. Gleviceras greenoughi sensu HAUER is difficult to correlate Meanwhile by comparison with established successions with the standard NW european zonation. Indeed the in the Lienz (BLAU & MEISTER, 1991), Salzburg and Rötel- usually admitted vertical distribution of the genus Gle- stein areas (MEISTER & BÖHM, 1993) we can propose to

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Text-Fig. 17. Faunal composition and paleogeographical affinities.

181 ©Geol. Bundesanstalt, Wien; download unter www.geologie.ac.at gather the species in several hypothetical levels. Each as- “representativity” of the Phylloceratidae, Juraphyllitidae semblage proposed here is characterized by specimens and Lytoceratidae in these “Ammonitico Rosso” facies. which have been collected together in a well determined Moreover in each assemblage the diversity is rather high: 4 tectonic block. to 6 taxa. For the paleogeographical affinities, the fauna is clearly Ibex Zone dominated by the Tethyan ammonites with an episode, from the Late Hettangian to the Late Sinemurian, of de- Luridum subzone creasing appearance and nearly disappearance of the gr. geyeri level ubiquitous ammonites. We have here considered Schlothei- The Carixian is only reliably attested by the presence of mia marmorea (OPPEL), Lytoceras ssp. and Arnioceras ssp. as Androgynoceras gr. geyeri, a species indicating the Middle potential ubiquitous forms. Carixian. In the Pliensbachian, the faunal ratio in the algovianum J. (Harpophylloceras) eximius and some Phylloceras sp. are al- horizon is almost the same in Wetzsteingraben, or in Rötel- so probably coming from this Middle Carixian assem- stein (MEISTER & BÖHM, 1993) and in the Lienz area (BLAU & blage. MEISTER, 1991). It shows a relatively homogeneity from the South to the North of the Upper Austroalpine unit. DOMERIAN SUBSTAGE Margaritatus Zone Stokesi subzone 6. Conclusion gr. isseli level This paper is the first attempt to present a precise bio- The presence of Amaltheus stokesi, P. (Calliphylloceras) bicico- stratigraphy for the Late Hettangian–Sinemurian of the lae and Partschiceras gr. striatocostatum, Juraphyllites libertus and Adnet quarries and to provide new elements for the corre- Protogrammoceras gr. isseli in the same assemblage charac- lations with the other parts of the western Tethys. But the terizes the Stokesi subzone. studies for the Tethyan Sinemurian still remain too discon- Gibbosus subzone tinuous. Moreover each outcrop (quarry) is charaterized by an original assemblage which does not allow detailed algovianum level comparisons and correlations as well at a local as at a This biochronological unit is represented by the asso- larger scale. Indeed the events recorded during the ciation of Arieticeras algovianum, Leptaleoceras aff. accuratum, P. Sinemurian in this part of the Tethys seem to be rather he- (Paltarpites) sp., Amaltheus margaritatus, Partschiceras gr. striato- terogeneous and stochastic, perhaps reflecting a com- costatum and Phylloceras gr. frondosum – hebertinum. plex structuration of the Liassic platforms. Only further * detailed studies of new regions will provide precisions. The faunal ratio (Text-Fig. 17) must be taken with cau- tion because of very discontinuous informations for the considered period and because of the very irregular num- Acknowledgements ber of specimens collected in each assemblage. Never- Dr. CHRISTIAN MEISTER thanks very much the Fonds National Suisse de theless the faunal compositions mainly show the weak la Recherche Scientifique for its support (No 20-39394.93).

Fig. 6: Juraphyllites nardii (MENEGHINI). Plate 1 Adnet, quarry 28, bed 100. Raricostatum zone. Figs. 7, 8: Juraphyllites sp. Fig. 7: Adnet, quarry 28, ex situ between beds Fig. 1: Phylloceras sp. 4–16a. Adnet, quarry 31, bed 10. ? Bucklandi – Semicostatum zones. Angulata to ? Bucklandi zones. Fig. 8: Adnet, quarry 38, bed 100. Obtusum zone. Fig. 2: Juraphyllitidae sp. Adnet, quarry 31, bed 10. Figs. 9,12: Partschiceras gr. striatocostatum (MENEGHINI). Angulata to ? Bucklandi zones. Fig. 9: Wetzsteingraben, associated with Arietice- ras gr. algovianum (OPPEL). Fig. 3: Phylloceras cylindricum (SOWERBY). Margaritatus zone. Adnet, quarry 38, bed 100. Fig. 12: Glasenbach, bed 3. Obtusum zone. Semicostatum ? – Obtusum zones. Fig. 10: J. (Harpophylloceras) eximius (HAUER). Fig. 4: P. (Zetoceras) sp. Wetzsteingraben, ex situ. Adnet, quarry 38, ex situ. ? Ibex zone. ? Obtusum zone. Fig. 5: Juraphyllites libertus (GEMMELLARO). Fig. 11: P. (Calliphylloceras) bicicolae (MENEGHINI). Wetzsteingraben, associated with Protogrammoceras gr. Wetzsteingraben, associated with Protogrammoceras isseli (FUCINI). gr. isseli (FUCINI). Margaritatus zone. Margaritatus zone.

All the ammonites are in natural size and come from the Museum of Adnet and the Natural History Museum of Geneva.

182 ©Geol. Bundesanstalt, Wien; download unter www.geologie.ac.at

183 ©Geol. Bundesanstalt, Wien; download unter www.geologie.ac.at

Plate 2

Figs. 1,6: Adnethiceras adnethicus (HAUER). Adnet, quarry 28, 1: bed 5 and 6: bed 12. ? Bucklandi – ? Semicostatum zones. Figs. 2,3: Derolytoceras sp. Adnet, quarry 38, bed 100. Obtusum zone. Figs. 4,7–9: Schlotheimia marmorea (OPPEL). Adnet, quarry 31, bed 10. Angulata to ? Bucklandi zones. Fig. 5: Angulaticeras (Boucaulticeras) sp. Adnet, quarry 41, bed 10. Semicostatum – ? Obtusum zones.